Characterization of Secondary Organic Aerosol Tracers Over Tianjin

Subscriber access provided by Nottingham Trent University

Article

Characterization of Secondary Organic Aerosol Tracers Over Tianjin, North China During Summer to Autumn Yu Wang, Chandra Mouli Pavuluri, Pingqing Fu, Peisen Li, Zhichao Dong, Zhanjie Xu, Hong Ren, Yanbing Fan, Linjie Li, Yanlin Zhang, and Cong-Qiang Liu ACS Earth Space Chem., Just Accepted Manuscript • DOI: 10.1021/ acsearthspacechem.9b00170 • Publication Date (Web): 22 Aug 2019 Downloaded from pubs.acs.org on August 27, 2019

Just Accepted “Just Accepted” manuscripts have been peer-reviewed and accepted for publication. They are posted online prior to technical editing, formatting for publication and author proofing. The American Chemical Society provides “Just Accepted” as a service to the research community to expedite the dissemination of scientific material as soon as possible after acceptance. “Just Accepted” manuscripts appear in full in PDF format accompanied by an HTML abstract. “Just Accepted” manuscripts have been fully peer reviewed, but should not be considered the official version of record. They are citable by the Digital Object Identifier (DOI®). “Just Accepted” is an optional service offered to authors. Therefore, the “Just Accepted” Web site may not include all articles that will be published in the journal. After a manuscript is technically edited and formatted, it will be removed from the “Just Accepted” Web site and published as an ASAP article. Note that technical editing may introduce minor changes to the manuscript text and/or graphics which could affect content, and all legal disclaimers and ethical guidelines that apply to the journal pertain. ACS cannot be held responsible for errors or consequences arising from the use of information contained in these “Just Accepted” manuscripts.

is published by the American Chemical Society. 1155 Sixteenth Street N.W., Washington, DC 20036 Published by American Chemical Society. Copyright © American Chemical Society. However, no copyright claim is made to original U.S. Government works, or works produced by employees of any Commonwealth realm Crown government in the course of their duties.

Page 1 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60

1 2 3 4 5 6 7 8 9

ACS Earth and Space Chemistry

Characterization of Secondary Organic Aerosol Tracers Over Tianjin, North China During Summer to Autumn Yu Wang1, Chandra Mouli Pavuluri1*, Pingqing Fu1, Peisen Li1, Zhichao Dong1, Zhanjie Xu1, Hong Ren1, Yanbing Fan1, Linjie Li2, Yan-Lin Zhang3, and Cong-Qiang Liu1 1Institute

2LAPC,

of Surface-Earth System Science, Tianjin University, Tianjin 300072, China.

Institute of Atmospheric Physics, Chinese Academy of Sciences, Beijing 100029, China

3Yale-NUIST

Center on Atmospheric Environment, Nanjing University of Information Science and

10 11 12

Technology, Nanjing 10044, China.

13

ABSTRACT: To characterize secondary organic aerosols (SOA) over the Tianjin region, we

14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32

studied the SOA tracers derived from isoprene, α/β-pinene, β-caryophyllene and aromatics in PM2.5 collected at an urban site and a background site over Tianjin, North China during summer to autumn 2018. Concentrations of total isoprene SOA tracers were twice those of α/β-pinene in summer, while they were the opposite in autumn, followed by β-caryophyllinic acid and 2,3dihydroxy-4-oxopentanoic acid (2,3-DHOPA), the only tracers derived from β-caryophyllene and toluene, respectively. The isoprene and α/β-pinene SOA tracers were abundant in summer whereas β-caryophylinic acid and 2,3-DHOPA dominated in autumn. Temporal variations and linear relations of SOA tracers with ambient temperature and molecular markers (levoglucosan and hopanes) together with the air mass trajectories implied that the SOA derived from terrestrial vegetation and marine biota and biomass burning was high in summer and autumn, respectively, while that derived from fossil fuel combustion and its processing during longrange atmospheric transport were significant in both seasons. The estimated SOA derived from aromatics was found to be most abundant, followed by that from sesquiterpenes, monoterpenes and isoprene, respectively. The contribution of total SOC to OC and WSOC varied between 4.16% and 23.7% and 6.28-30.7%, respectively, in which biogenic SOC accounted for about 50% in summer and 40% in autumn, indicating significant loading of SOA over Tianjin, North China.

33 34 35 36

atmospheric transport, North China INTRODUCTION Organic aerosols (OA) account for a significant fraction (20-50%) in midlatitudes and an even

37 38

dominant fraction (up to 90%) in forested areas.1 They have a severe impact on the Earth’s climate system directly by absorbing and scattering solar radiation and indirectly by acting as

KEYWORDS: Secondary organic aerosols, biogenic emissions, biomass burning, long-range

ACS Paragon Plus Environment

ACS Earth and Space Chemistry 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60

Page 2 of 27

39

cloud condensation nuclei (CCN).2 OA can also adversely affect human health3, 4 and play an

40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56

important role in atmospheric chemistry.5 They are emitted directly from natural and anthropogenic sources such as fossil fuel combustion, biomass burning, soil suspension, biological species and agricultural waste (primary, POA) and formed by reactions of volatile organic compounds (VOCs) that are emitted from a variety of sources including vegetation, biomass burning and fossil fuel combustion with O3, OH and NO3 radicals and subsequent nucleation and/or condensation onto pre-existing aerosols of the resulted low-volatility compounds in the atmosphere (secondary, SOA).6-10 SOA accounts for ~60% of OA globally and even more on a regional scale.1 Vegetation releases large amounts of VOCs, including isoprene, monoterpenes, sesquiterpenes, and oxygenated hydrocarbons.11, 12 On a global scale, biogenic VOCs were estimated to be 1150 TG yr-1 with a predominance of isoprene (44%) followed by monoterpenes (11%)11, whereas anthropogenic VOCs were only 110 Tg yr-1, in which aromatics account for 13%.13 Thus, the SOA formed from biogenic emissions is believed to be larger than that from anthropogenic sources.1 However, the contribution of SOA from anthropogenic sources often exceeds 50% in most populated regions, including Asia, due to human activities.14 Besides, the anthropogenic emissions in urban localities might accelerate the oxidation of BVOCs and enhance the SOA formation.15, 16 Specific molecular marker compounds (tracers) could provide insights into the origins of

57 58 59 60 61 62 63 64 65 66 67 68 69 70 71

OA and precursors of SOA as well as its formation processes that influence SOA evolution and spatiotemporal distribution in the atmosphere. Isoprene-derived SOA (SOAI) has been regarded as negligible due to the high volatility of its known reaction products and the low SOA yield,17 despite its large flux.12 However, identification of two diastereoisomeric 2methyltetrols in Amazonian rain forest aerosols as isoprene oxidation products by Claeys et al.18 has changed the way the scientific community thinks of SOAI. Furthermore, the discovery of isoprene epoxydiols (IEPOX) formation by reactions of isoprene with OH and HO2 radicals (HO2-channel)19-21 under low-NOx (NOx = NO + NO2) conditions, and 2-methylglyceric acid (2-MGA) and methacrylic acid epoxide (MAE) by reactions with NO and NO2 radicals (NOxchannel)22, 23 under high-NOx conditions, and the influence of aerosol acidity24 and relative humidity23 on their yield, has expanded the understanding of the formation processes of SOAI. Currently, isoprene is believed to be a large biogenic source of SOA loading, and the contribution of SOAI is estimated to be 2-19.2 Tg yr-1 on the global scale,18, 25 accounting for about 70% of the total SOA.26 Monoterpene- (SOAM) and sesquiterpene-derived SOA (SOAS) are also considered

72 73 74 75 76

significant contributors to SOA loading in the atmosphere. Previous experiments on monoterpene oxidation under natural or artificial sunlight found the product species with either endocyclic double bonds (in the case of α-pinene) or exocyclic double bonds (in the case of βpinene), which leads to the understanding of SOAM formation processes.27 It has been established that cis-pinonic acid (PNA) and pinic acid (PA) are the first-generation major 2


Page 3 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60


77

products formed by the reaction of α- and β-pinene with O328 and OH radicals.29 PNA and PA

78 79 80 81 82 83 84 85 86 87 88

can be further photooxidized to high-generation products such as 3-methyl-1,2,3butanetricarboxylic acid (3-MBTCA).30 Moreover, it has been found that highly oxygenated products such as 3-hydroxyglutaric acid (3-HGA) are formed by photooxidation of α-pinene in the presence of NOx through reactions that involve O3 and OH radicals.31 β-caryophyllinic acid (β-CPA) has been identified as a specific tracer for SOAS.32 The amount of biogenic SOA is estimated to be in the range of 9-50 Tg yr-1 using global bottom-up models1, and up as high as 185 Tg yr-1 by top-down models.33 Also, 2,3-dihydroxy-4-pentanoic acid (2,3-DHOPA) has been found to be produced by photooxidation of toluene and is considered a tracer for SOA derived from anthropogenic aromatics (SOAA)34, 35 and the contribution of SOAA is reported to be highly significant and even larger than that of biogenic SOA in some locations.35, 36 Kleindienst et al.35 estimated the contributions of biogenic SOA as well as anthropogenic

89 90 91 92 93 94 95 96 97 98 99 100 101 102 103

SOA using the mass fractions of the tracers obtained from photochemical oxidation of isoprene, α-pinene and β-caryophyllene and toluene in chamber experiments. Furthermore, the SOA tracers have been reported in ambient aerosols from forested or mountain18, 35, 37-42 and urban areas15, 36, 43-45 as well as the Arctic region46, which provides insights on SOA formation and transformation processes and its loading at those locales. Atmospheric aerosol loading is commonly observed to be high in East Asia. China is the largest developing country in this region and its economy has been growing at a very rapid rate over the past decades. Currently, fine (PM2.5) aerosol concentrations exceed the national air quality standards in most cities47 and have become a serious environmental problem in China. In fact, the contribution of SOA to PM2.5 and OA has been estimated to be up to 35% and 71%, respectively,48 and thus SOA plays an important role in deteriorating the air quality in China. Previous modelling studies predicted that biogenic VOCs are the major contributors of SOA in China49, 50 but groundbased observation studies, particularly in North China, suggest that anthropogenic aromatics are the largest SOA contributors.36, 51 Studies on biogenic and anthropogenic SOA tracers and their formation processes and

104 105 106 107 108 109 110 111 112 113 114

loading are very limited in North China,15, 36, 51, 52 particularly in the Tianjin-Hebei region, where high aerosol loading is prevalent and often suffers from haze events,53, 54 and where the air quality is poor.55 Tianjin is one of the fastest developing regions in China, and hence the anthropogenic pollutant emissions are very high. On the other hand, the Tianjin region is covered with rich vegetation, including agricultural lands and forests. In addition, Tianjin is located adjacent to Bohai sea and hence, the impact of marine biogenic emissions on Tianjin aerosols is significant. Therefore, the potential for VOC emissions from biogenic and anthropogenic sources, including biomass burning, is high in this region and thus, the formation of SOA is also high. Consequently, it is highly necessary to investigate the organic molecular composition of SOA tracers in Tianjin aerosols. In this study, we aim to characterize the chemical composition and abundances of 3



Page 4 of 27

115

isoprene-, α/β-pinene-, β-caryophyllene- and toluene-derived SOA tracers in atmospheric fine

116 117 118 119 120 121 122 123 124

(PM2.5) aerosols collected at an urban and a background site over Tianjin, North China during summer to autumn 2018. Also, we intend to estimate the contributions of secondary organic carbon (SOC) derived from biogenic and anthropogenic VOCs to organic carbon (OC) and water-soluble OC (WSOC) in the PM2.5. The results will be discussed in terms of SOA origins, formation processes and loading over Tianjin and thus, this study provides a baseline data of SOA that will help to improve model simulations.

125 126 127 128 129 130 131 132 133 134 135 136 137 138 139 140 141 142 143

(Nankai district (ND) located at 39.11°N, 117.18°E) and a background site (Haihe Education Park (HEP) at 39.00°N, 117.32°E), which are 23 km away from each other in Tianjin (see Fig. S1 in the supporting information), a city located on the lower reaches of Haihe river and adjacent to Bohai sea with a population of ~13 million (https://en.wikipedia.org/wiki/Tianjin). Coal is the main source of energy and the industrial terminal energy consumption accounts for ~66% of the total energy consumption. Agricultural activity is high in northern parts of the Tianjin region, which is also covered with mountains and dense forests. Therefore, the influence of fossil fuel combustion emissions is high at ND, whereas biogenic and/or biomass burning emissions as well as sea breezes greatly influence HEP. The regional climate over Tianjin is strongly affected by the East Asian monsoon that influences the origins of the longrange transported air masses that arrive in Tianjin. The sampling was performed on the rooftop of a 7-storey building at Tianjin University (TJU) Weijin Road campus (ND; n = 39) and a 6storey building in TJU Peiyang Park campus (HEP; n = 20) using pre-combusted (450℃, 4h) quartz fiber filters (Pall, 2500QAT-UP) and a high-volume air sampler (Tisch Environmental, TE-6070DX) for ~72 h each sample during summer to autumn (5 July to 30 October) 2018. The filter samples were placed in a pre-combusted glass jar with a Teflon-lined screw cap and stored at -20℃ in darkness prior to analysis. One blank filter sample was also collected in each season following the same procedure without the pump switched on. Determination of organic tracers. PM2.5 samples were extracted and derivatized

144 145 146 147 148 149 150 151 152

following the procedure described elsewhere.46 Briefly, filter aliquots were firstly extracted with 10 ml dichloromethane/methanol (2:1; v/v, ANPEL Laboratory Technologies (Shanghai) Inc, 99.9%) for three times under ultrasonication for 10 min each. The extracts were filtered through quartz wool packed in a Pasteur pipette (ANPEL Laboratory Technologies (Shanghai) Inc) and concentrated to about 100 l under rotary evaporation and then blown to dryness under pure nitrogen gas. The organic compounds were then reacted with 60 l of N, O-bis(trimethylsilyl)trifluoroacetamide (BSTFA) in the presence of 1% trimethylchlorosilane (Sigma-Aldrich) and 10 l pyridine (Sigma-Aldrich, 99.9%) at 70℃ for 3 hours to derivatize the carboxyl group trimethylsilyl (TMS) esters and OH to TMS ethers. The derivatives were

EXPERIMENTAL SECTION Sample collection. PM2.5 samples were collected simultaneously at an urban site

4


Page 5 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60


153

then diluted by adding 40 l of n-hexane containing 1.43 ng l-1 of an internal standard (C13 n-

154 155 156 157 158 159 160 161 162 163 164

alkane, to determine the relative response) before injecting into a gas chromatograph/mass spectrometer (GC/MS, Hewlett-Packard 7890A GC coupled with 5975C MSD), equipped with a split/splitless injection and fused silica capillary column (DB-5MS, 30 m × 0.25 mm i.d., 0.25 m film thickness). The derivatized samples were injected into the GC in a splitless mode at an injector temperature of 280C and the compound separation was carried out on a capillary column with the GC oven temperature programmed from 50C (2 min) to 120C (at 15 C min−1) and then to 300C (at 5C min−1) with a final isothermal hold at 300 C for 16 min. Helium was used as a carrier gas. The MS was operated in the electron ionization (EI) mode at 70 ev and scanned in the m/z range of 50 to 650 Da. Data were processed with Chemstation software. Individual compounds of TMS derivatives of SOA tracers (and other marker species) were

165 166 167 168 169 170 171 172 173 174 175 176 177 178

identified by comparison of mass spectra with those of authentic standards or literature data. PNA, PA, 3-HGA and 2,3-DHOPA were quantified using their authentic standards, while the other SOA tracers were quantified using surrogate compounds: erythritol for 2-methyltetrols (2-MTLs), C5-alkene triols and 2-methylglyceric acid (2-MGA),18 PNA for 3-MBTCA, and PA for β-CPA,41 due to lack of standards. The method detection limits for erythritol, PNA, PA, 3-HGA and 2,3-DHOPA were 0.03, 0.08, 0.13, 0.06 and 0.05 ng m-3, respectively, with the used sample volume of 30.0 m3. Recoveries for authentic standards or surrogates that were spiked on to pre-combusted quartz filters were found to be more than 80%. Based on duplicate sample analysis, the analytical error was generally less than 10%. Field blank filter samples were treated following the same procedures for quality assurance and no target SOA tracers, except for 2-HGA, were detected. The 2-HGA only appeared in one summer filter blank, but its concentration was less than 1% of that in actual samples and the data presented here was corrected for the blank, but not for recoveries. Measurements of OC, EC, and WSOC. OC and EC were measured using the Sunset

179 180 181 182 183 184 185 186 187 188 189

Laboratory OC/EC Analyzer (Sunset Laboratory Inc., USA) following the Interagency Monitoring of Protected Visual Environments (IMPROVE) thermal/optical evaluation protocol56 and assuming the carbonate carbon to be negligible.57 Briefly, an aliquot of filter sample (1.5 cm2) was punched and inserted into a quartz boat inside the thermal desorption chamber of the analyzer and then combusted with stepwise heating. The evolved CO2 was measured directly by a non-dispersive infrared (NDIR) detector system and the transmittance of light through the filter punch was used for OC correction. WSOC was measured using TOC analyzer (TOC-Vcsh, Shimadzu, Japan) after extracting an aliquot of filter samples (14 mm disc in diameter) into 20 ml organic free Milli Q water under ultrasonication for 20 min.57 Based on duplicate sample analysis, the analytical uncertainty in all measurements was generally less than 5%. All the concentrations reported here were corrected for field blanks.

5



Page 6 of 27

190 191 192 193 194 195 196 197 198 199 200 201 202 203 204 205 206 207 208 209 210 211 212 213 214 215

Estimation of SOC. The isoprene-, monoterpene-, sesquiterpene- and aromatics-derived SOC was estimated using a tracer-based method proposed by Kleindienst et al.,35 using the measured concentrations of tracers in PM2.5 and the laboratory-derived tracer mass fraction (fSOC) factors of 0.155 ± 0.039 for isoprene, 0.231 ± 0.111 for α-pinene and 0.023 ± 0.0046 for -caryophyllene and 0.0079 ± 0.0026 for toluene by the following equation: fSOC = Σi[tracer]/[SOC] where Σi[tracer] is the sum of the concentrations of the selected suite of tracers for the same precursor in g m-3. This technique was developed using a series of chamber experiments conducted under relatively high NOx (0.11-0.65 ppm) conditions. However, it has been reported that the fSOC derived for isoprene (range 0.117-0.231, ave. 0.156) in the absence of NOx58 is similar to that obtained under high NOx conditions, although the NOx influence of the fSOC for other VOCs is not clear. Furthermore, the concentration of NO2 in Tianjin ranged from 0.014 to 0.37 ppm with an average of 0.022 ppm during the campaign period (see Fig. 1b). Hence, we consider the tracer-based method highly applicable for this study. It should also be noted that Kleindienst et al.35 derived the fSOC by using ketopinic acid as the surrogate for quantification of all the SOA tracers, whereas, as detailed earlier, the SOA tracers in this study were quantified using authentic standards, together with some surrogates that were further quantified by GC-FID. Such differences could result in some degree of uncertainty. Furthermore, three compounds including 2-MGA and two 2-MTLs were used as tracers for SOAI estimation, and -CPA and 2,3-DHOPA were used as tracers for SOAS and SOAA estimation, respectively, in this study, which are the same as those used in Kleindienst et al.35. Although Kleindienst et al. reported nine tracers for SOAM estimation, we used only four compounds such as 3-HGA, PNA, PA, and 3-MBTCA determined in this study. However, we consider that the uncertainties due to the differences in the tracers used for SOA estimation should be within the uncertainties raised by the tracer-based approach itself (22–54%) due to the standard deviation of fSOC mentioned above.

216 217 218 219 220 221 222 223 224 225 226 227 228 229 230

RESULTS AND DISCUSSION Meteorology, oxidants, and backward air mass trajectories. Hourly averaged meteorological data of Tianjin available online were downloaded from a website; https://darksky.net/forecast/39.1236,117.1981/si12/en, and the oxidants (O3 and NO2) data were downloaded at http://beijingair.sinaapp.com. Averaged ambient temperature and relative humidity (RH) as well as O3 and NO2 for each sample period during the campaign are presented in Fig. 1a,b. The ambient temperature ranged from 25.0C to 31.6C with an average of 28.0  2.12C in summer and 11.6-27.0C (average 18.2  4.81C) in autumn and the RH ranged from 58.0-82.7% (72.3  6.59%) and 31.8-73.2% (49.4  12.6%), respectively. While the wind speed varied between 2.14 m s-1 to 5.15 m s-1 with an average of 3.17  0.78 m s-1 in summer and 1.76-4.99 m s-1 (3.28  0.92 m s-1) in autumn. Concentrations of O3 and NO2 were 91.7   g m-3 and 34.0   g m-3, respectively, in summer and 50.1   g m-3 and 49.4  9.80 g m-3 in autumn. Cluster analysis of the air masses situated at 500 m above ground level over Tianjin for 6


Page 7 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60

231 232 233 234 235 236 237


Figure 1. Temporal variations of (i) meteorological parameters: ambient temperature and relative humidity (RH) (a) and (ii) concentrations (g m-3) of oxidants: O3 and NO2, (b) at Tianjin, and (iii) concentrations (g m-3) of bulk contents: EC, OC and WSOC, (c) and (iv) those (ng m-3) of molecular markers: levoglucosan and hopanes (C27-C32) (d) and (v) SOAI (e,f), SOAM (g,h), SOAS (i) and SOAA (j) tracers in PM2.5 collected at an urban site (Nankai District, ND) and a background site (Haihe Education Park, HEP) in Tianjin during summer to autumn 2018. See text for abbrevations.

7



Page 8 of 27

238

one-month period each during the campaign was conducted using the five-day backward air

239 240 241 242 243 244 245 246 247

mass trajectories data obtained from NOAA HYSPLIT modeling system (ftp://arlftp.arlhq.noaa.gov/pub/archives/gdas1). The computed plots are provided in the SI (Fig. S2). The results show that about 94% of the air masses that arrived in Tianjin in July originated from the sea of Japan, East China Sea and/or western North Pacific Ocean, whereas, only 19.5% of the air masses originated from the East China Sea in August and the rest of the air masses originated from Siberia, Mongolia or China mainland in summer (Fig. S2a,b). In autumn, about 50% and 73% of the air masses originated from Siberia in September and October, respectively, and the rest originated from northern China mainland (Fig. S2c,d). Carbonaceous components. A summary of concentrations of elemental carbon

248 249 250 251 252 253 254 255 256 257 258 259 260

(EC), OC and WSOC observed at ND and HEP in Tianjin, North China in summer and autumn is presented in Table 1. Their temporal variations during the campaign are depicted in Fig. 1c. Concentrations of EC and OC ranged from 0.11 gC m-3 to 0.54 gC m-3 with an average of 0.28  0.13 gC m-3 and 1.37-8.89 gC m-3 (average 3.01  1.64 gC m-3) at ND (n = 39) and 0.09-0.81 gC m-3 (0.44  0.21 gC m-3) and 0.85-9.86 gC m-3 (3.86  2.20 gC m-3) at HEP (n = 20), respectively, during the campaign. While WSOC ranged between 1.14-6.47 gC m-3 (2.27  1.08 gC m-3) at ND and 0.66-6.11 gC m-3 (2.62  1.34 gC m-3) at HEP. The average relative abundance of WSOC in OC was found to be 78.0  12.3% at ND and 72.1  17.8% at HEP. Concentrations of EC, OC, and WSOC observed in summer at ND (Table 1) were found to be lower than those (0.59, 5.25 and 3.48 g m-3 in daytime and 0.74, 4.62 and 2.63 g m-3 in the nighttime, respectively) reported in PM2.5 collected from the same site in July 2016.59 This is consistent with the recent decreasing trend in aerosol loading over China.60 WSOC can be directly emitted from biomass burning61 and also formed by oxidation of

261 262 263 264 265 266 267 268 269 270 271 272 273 274 275

VOCs in the atmosphere.62 The mass ratio of WSOC to OC has been considered a measure of photochemical processing (aging) during long-range atmospheric transport,63 if the influence of biomass burning is insignificant. Interestingly, the average WSOC/OC found at ND in summer (Table 1) was higher than that (63%) reported in summer 2016 from the same site.59 Such high abundance of WSOC should be due to either enhanced emission from biomass burning and/or secondary formation from VOCs. As can be seen from Fig. 1d, concentrations of levoglucosan, an excellent marker for biomass burning,64 were found to be extremely low at both the sites in summer, which suggests that the contribution of OA (including WSOC) from biomass burning was not significant. On the other hand, the air masses that arrived in Tianjin during summer, particularly in July when the OC, WSOC and SOA tracers peaked, mostly originated from the oceanic region (Fig. S2a,b), which means they should have been enriched with marine biogenic emissions and subsequently aged during long-range atmospheric transport. Therefore, the enhanced WSOC/OC implies that the loading of SOA is increasing over China, despite a decrease in overall aerosol burden in recent years, probably due to the increased oxidation capacity of the atmosphere. It is likely because O3 concentrations 8


Page 9 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46

276 277


Table 1. Summary of concentrations of bulk contents, SOA tracers and contributions of their C contents to OC and WSOC in PM2.5 at ND and HEP over Tianjin, North China in summer and autumn 2018.a ND HEP Summer (n = 19) Autumn (n = 20) Summer (n =10) Autumn (n =10) Concentration Per cent C in Concentration Per cent C in Concentration Per cent C in Concentration Per cent C in Range OC WSOC Range OC WSOC Range OC WSOC Range OC WSOC Ave  SD Ave  SD Ave  SD Ave  SD Bulk carbonaceous contents (gC m-3) EC 0.11–0.31 0.21–0.54 0.09–0.59 0.41–0.81 0.18  0.06 0.37  0.11 0.28  0.16 0.59  0.13 OC 1.37–3.25 1.48–8.89 0.85–4.34 3.01–9.86 2.16  0.55 3.83  1.91 2.44  1.20 5.28  2.07 WSOC 1.14–3.12 85.5 1.16–6.47 70.8 0.66–3.73 86.6 1.48–6.11 57.6 1.85  0.55 2.66  1.31 2.16  1.17 3.08  1.41 SOA Tracers (ng m-3) Isoprene-derived SOA tracers 2-Methylthreitol 0.14–3.15 0.02 0.02 0.11–1.05 0.01 0.01 0.32–6.16 0.03 0.03 0.22–0.83 0.004 0.01 1.08  0.82 0.43  0.25 1.88  1.84 0.45  0.18 2-Methylerythetol 0.15–9.89 0.06 0.07 0.26–3.28 0.01 0.02 0.81–19.2 0.10 0.11 0.38–1.48 0.01 0.01 3.05  2.62 1.06  0.74 6.16  6.75 0.79  0.33 0.29–13.0 0.08 0.09 0.39–4.33 0.02 0.03 1.13–25.3 0.13 0.14 0.61–2.31 0.01 0.02 2-MTLs 4.13  3.43 1.49  0.98 8.05  8.54 1.23  0.51 cis-2-MTHB 0.22–12.1 0.06 0.06 0.03–2.03 0.01 0.01 0.30–12.3 0.07 0.07 0.06–0.56 0.002 0.004 2.65  2.99 0.54  0.57 4.08  4.73 0.24  0.15 3-MTHB 0.10–6.43 0.03 0.03 0.01–1.07 0.00 0.01 0.14–6.49 0.03 0.04 0.03–0.25 0.001 0.002 1.42  1.58 0.27  0.30 2.12  2.49 0.120.06 trans-2-MTHB 0.70–42.7 0.19 0.22 0.06–7.00 0.03 0.04 0.93–42.3 0.22 0.25 0.15–1.69 0.01 0.01 9.16  10.5 1.76  1.98 13.9  16.2 0.74  0.47 1.02–61.2 0.28 0.31 0.11–10.1 0.04 0.06 1.37–60.8 0.32 0.36 0.27–2.50 0.01 0.02 C5-Alkene triols 13.2  15.0 2.57  2.86 20.1  23.5 1.10  0.67 2-MGA 0.22–2.44 0.02 0.02 0.16–2.72 0.01 0.02 0.30–3.03 0.02 0.02 0.22–2.84 0.01 0.02 0.91  0.58 1.02  0.64 1.31  0.91 1.22  0.80 Subtotal 2.07–76.3 0.37 0.42 0.70–15.5 0.07 0.10 2.80–88.6 0.47 0.52 1.09–7.66 0.03 0.05 18.3  18.7 5.07  4.11 29.5  32.6 3.56  1.88 Monoterpenes-derived SOA tracers PNA 0.13–0.78 0.01 0.01 0.12–1.87 0.01 0.01 0.03–0.64 0.01 0.01 0.21–1.59 0.01 0.02 0.33  0.15 0.47  0.37 0.28  0.22 0.72  0.51 PA 0.76–8.32 0.07 0.08 0.70–9.06 0.05 0.07 0.81–5.90 0.06 0.07 0.52–3.91 0.02 0.03 2.57  1.92 2.88  1.74 2.55  1.97 1.29  1.13 3-HGA 0.83–5.26 0.04 0.05 0.29–4.29 0.02 0.03 1.02–5.95 0.05 0.05 0.31–3.44 0.01 0.02 2.17  1.19 1.71  1.02 2.89  2.02 1.72  1.01 3-MBTCA 1.43–8.42 0.08 0.09 0.82–8.05 0.04 0.06 1.62–11.3 0.10 0.11 0.80–8.33 0.03 0.06 3.45  1.83 2.88  1.49 5.28  3.73 3.18  2.04 Subtotal 3.71–19.87 0.19 0.22 3.69–16.9 0.12 0.17 3.93–22.4 0.21 0.24 3.22–13.7 0.07 0.13 8.52  4.39 7.94  3.30 11.0  7.82 6.91  3.37 Sesquiterpenes-derived SOA tracer β-Caryophyllinic acid 0.53–2.38 0.04 0.04 0.35–5.78 0.03 0.04 0.56–2.65 0.04 0.05 0.80–4.65 0.03 0.05 1.26  0.50 1.72  1.44 1.44  0.80 2.53  1.38 Total SOABio tracers 6.32–98.6 0.60 0.69 5.15–31.1 0.22 0.31 7.33–113 0.72 0.81 5.35–20.5 0.13 0.24 28.0  22.9 14.7  7.06 41.9  40.7 13.0  5.27 Aromatics-derived SOA tracer 2,3-DHOPA 0.23–1.90 0.02 0.02 0.24–6.11 0.02 0.02 0.34–3.11 0.03 0.03 1.05–2.97 0.02 0.03 0.86  0.53 1.75  1.49 1.42  0.94 2.02  0.75 Total SOA tracers 6.75–100 0.62 0.71 5.90–37.2 0.23 0.33 8.00–116 0.75 0.84 6.40–22.5 0.15 0.26 28.9  23.1 16.5  8.00 43.3  41.5 15.0  5.51 SOC (g m-3) SOCI 0.01–0.10 1.43 1.64 0.004–0.03 0.48 0.67 0.01–0.18 2.21 2.48 0.01–0.03 0.31 0.55 0.03  0.02 0.02  0.01 0.06  0.06 0.02  0.01 SOCM 0.02–0.09 1.67 1.96 0.02–0.07 1.00 1.42 0.02–0.10 1.87 2.14 0.01–0.06 0.64 1.12 0.04  0.02 0.03  0.01 0.05  0.03 0.03  0.01 SOCS 0.02–0.10 2.48 2.90 0.02–0.25 1.73 2.48 0.02–0.12 2.61 3.02 0.03–0.20 1.98 3.48 0.05  0.02 0.07  0.06 0.06  0.03 0.11  0.06 SOCBio 0.05–0.29 5.58 6.50 0.04–0.36 3.21 4.57 0.05–0.39 6.70 7.65 0.06–0.27 2.93 5.15 0.12  0.06 0.13  0.08 0.17  0.12 0.16  0.07 SOCA 0.03–0.24 4.91 5.74 0.03–0.77 5.10 7.24 0.04–0.39 8.12 9.47 0.13–0.38 4.96 8.76 0.11  0.07 0.22  0.19 0.18  0.12 0.26  0.10 SOCTotal 0.10–0.50 10.5 12.2 0.07–1.13 8.31 11.8 0.13–0.74 14.8 17.1 0.20–0.57 7.89 13.9 0.23  0.12 0.35  0.26 0.35  0.24 0.41  0.15 aAve: average; SD: standard deviation; 2-MTLs (2-methyltetrols): 2-methylthreitol+2-methylerythetol; cis-2-MTHB: cis-2-methyl-1,3,4-trihydroxy-1-butene; 3-MTHB: 3-methyl-2,3,4-trihydroxy-1-butene; trans-2-MTHB: trans-2-methyl-1,3,4trihydroxy-1-butene; C5-alkene triols: cis-2-MTHB+3-MTHB+trans-2-MTHB; 2-MGA: 2-Methylglyceric acid; PNA: cis-pinonic acid; PA: pinic acid; 3-HGA: 3-hydroxyglutaric acid; 3-MBTCA: 3-methyl-1,2,3-tricarboxylic acid; 2,3-DHOPA: 2,3-dihydroxy-4-oxopentanoic acid; SOC: secondary organic carbon; SOCI, SOCM, SOCS and SOCA: SOC derived from isoprene, monoterpenes, sesquiterpenes and aromatics, respectively. Species



279

(about 30%) and the mass ratios of OC to EC over China, particularly in Beijing-Tianjin-Heibei

280 281

(BTH) region, were reported to be increasing annually in recent times.60, 65 Composition and abundances of SOA tracers. Molecular distributions of

282 283

isoprene-, /-pinene-, -caryophyllene- and toluene-derived SOA tracers determined in PM2.5 collected at ND (n = 39) and HEP (n = 20) over Tianjin are depicted in Fig. 2. Six isoprene

284 285 286 287 288 289 290 291 292 293 294 295 296 297 298

oxidation products including two 2-MTLs (2-methylthreitol and 2-methylerythritol), three C5alkene triols (cis-2-methyl-1,3,4-trihydroxy-1-butene, 3-methyl-2,3,4-trihydroxy-1-butene and trans-2-methyl-1,3,4-trihydroxy-1-butene), and 2-MGA were identified in Tianjin PM2.5 collected at both the sites. Concentrations of 2-methylerythritol were always higher by a factor of 2~3 than that of 2-methylthreitol at both the sites in Tianjin (Table 1). Averages of 2methylthreitol and 2-methylerythritol were found to be 0.75 ± 0.68 ng m-3 and 2.03 ± 2.13 ng m-3 at ND (n = 39) and 1.16 ± 1.47 ng m-3 and 3.47 ± 5.41 ng m-3 at HEP (n = 20), respectively, during the campaign. Those of the sums of C5-alkene triols were 7.76 ± 11.9 ng m-3 at ND and 10.6 ± 18.9 ng m-3 at HEP, with a high abundance of trans-2-methyl-1,3,4-trihydroxy-1-butene (5.37 ± 8.24 ng m-3 at ND and 7.33 ± 13.1 ng m-3 at HEP) followed by cis-2-methyl-1,3,4trihydroxy-1-butene (1.57 ± 2.35 ng m-3 and 2.16 ± 3.80 ng m-3) and 3-methyl-2,3,4trihydroxy-1-butene (0.83 ± 1.25 ng m-3 and 1.12 ± 2.00 ng m-3), respectively, at both the sites during the campaign. While the average of 2-MGA was 0.96 ± 0.61 ng m-3) at ND and 1.27 ± 0.83 ng m-3 at HEP. Four /-pinene oxidation products; PNA, PA, 3-HGA and 3-MBTCA were detected.

299 300 301 302 303 304 305 306 307 308 309 310

Averages of PNA and PA were found to be 0.41 ± 0.29 ng m-3 and 2.73 ± 1.81 ng m-3 at ND and 0.50 ± 0.45 ng m-3 and 1.92 ± 1.69 ng m-3 at HEP, respectively, during the campaign. While those of 3-HGA and 3-MBTCA were 1.93 ± 1.12 ng m-3 and 3.16 ± 1.67 ng m-3 at ND and 2.30 ± 1.67 ng m-3 and 4.23 ± 3.12 ng m-3 at HEP, respectively. The average abundance of the sum of isoprene-derived tracers (11.5 ± 14.8 ng m-3) was found to be slightly higher than that (8.22 ± 3.83 ng m-3) of /-pinene-derived tracers at ND, whereas at HEP, it was higher by a factor of ~2 (16.5 ± 26.1 ng m-3 and 8.96 ± 6.23 ng m-3, respectively) during the campaign. CPA, an oxidation product of -caryophyllene, and 2,3-DHOPA, an oxidation product of toluene, ranged from 0.35-5.78 ng m-3 (1.49 ± 1.10 ng m-3) and 0.23-6.11 ng m-3 (1.32 ± 1.20 ng m-3) at ND and 0.56-4.65 ng m-3 (1.99 ± 1.23 ng m-3) and 0.34-3.11 ng m-3 (1.72 ± 0.88 ng m-3) at HEP, respectively, during the campaign. It is noteworthy that all the biogenic SOA tracers, except PA, were found to be abundant

311 312 313 314 315 316

at HEP as compared to ND during the campaign (Fig. 2). It is likely because the emission of biogenic VOCs must be higher at HEP, where human activities are less and most of the area is covered with dense vegetation. Furthermore, such spatial distributions indicate that SOA loading over Tianjin must be significantly influenced by local emissions, in addition to the contribution from long-range transported airmasses. Interestingly, in consistence with that of biogenic SOA tracers, the average concentration of 2,3-DHOPA, an anthropogenic aromatics-


Page 10 of 27

Page 11 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60


317 318 319

at ND and HEP in Tianjin, North China during the campaign. See Table 1 for abbreviations.

320 321 322 323 324 325 326 327 328 329 330 331 332 333 334 335 336 337 338 339 340 341 342

derived SOA tracer, was also found to be higher at HEP than that at ND (Fig. 2), although its peak was at ND in autumn (Fig. 1j). Such high abundance of 2,3-DHOPA at HEP suggests that oxidants (OHx, O3, and NOx) that promote the SOA formation from both biogenic and anthropogenic VOCs loading should be higher at HEP. But it is unlikely, because the anthropogenic emissions including automobile exhaust in HEP must be lower than those in ND. Alternatively, the 2,3-DHOPA might be partly derived from biogenic and/or biomass burning sources as well, rather than fossil fuel combustion emissions alone. Concentrations of total SOAI tracers and SOAM observed in Tianjin PM2.5 (Table 1) are lower than those (averages 59 ± 32 ng m-3 and 30 ± 14 ng m-3, respectively, at Peking university (PKU) and 75 ± 43 ng m-3 and 32 ± 14 ng m-3 at Yufa) reported in the PM2.5 collected in summer 200752 and 200851 (140 ± 101 ng m-3 and 113 ± 63 ng m-3 at PKU and 215 ± 160 ng m-3 and 124 ± 48 ng m-3 at Yufa) from Beijing. However, concentrations of -CPA are closer to those (2.7 ± 1.0 ng m-3 at PKU and 3.9 ± 1.5 ng m-3 at Yufa in summer 2007) reported from Beijing. Similarly, the concentrations of total SOAI tracers in Tianjin (Table 1) are lower than those (averages 56.5 ng m-3 to 202 ng m-3) reported in summer 2012 from different (Urban, suburban, rural and remote) locations: Hailun, Tongyu, Beijing, Taiyuan, Dunhuang, Shapotou, Hefei, Wuxi, Qianyanzhou, Kunming, Xishuanbanna, Nam Co and Sanya, but comparable to that (average 26.2 ng m-3) reported from a rural site (Linzhi) over China.36 In contrast, the concentrations of total SOAM tracers, -CPA, and 2,3-DHOPA in Tianjin PM2.5 (Table 1) are comparable or even higher than those (averages 0.66 ng m-3 to 9.61 ng m-3, 0.06-3.05 ng m-3 and 0.40-2.40 ng m-3, respectively) reported from 8, 6 and 7 locations, respectively, listed above and slightly lower than those (13.8 ng m-3 to 20.2 ng m-3, 4.98-14.9 ng m-3 and 2.62-5.22 ng m-3, respectively) reported from rest of the sites located in North, Northeast and East China

Figure 2. Molecular distributions of biogenic and anthropogenic secondary organic aerosol (SOA) tracers

11



Page 12 of 27

343 344

in summer 2012.36 On the other hand, the concentrations of first-generation SOAI tracers, 2-MTLs, in Tianjin

345 346 347 348 349 350 351 352 353

are lower than those reported in forest aerosols collected from Hokkaido, Japan (average 78 ng m-3)66 and Mt. Tai, China (average 98 ng m-3)40 in spring and/or summer periods, where the emission of isoprene from local higher plants is high. However, they are higher than those (1.02±1.17 ng m-3) reported in remote marine aerosols from Okinawa island, Japan, which were considered to be influenced by the aged air masses transported from Asia.67 Such comparisons suggest that the sources and/or source strength of SOA over Tianjin are significantly distinct from other locations over the northern China plain, and that the Tianjin OA might have been influenced by long-range transported aged air masses. Temporal and seasonal variations. Temporal variations in concentrations of SOA

354 355 356 357 358 359 360 361 362 363 364 365 366

tracers determined in PM2.5 at ND and HEP in Tianjin during the campaign are depicted in Fig. 1e-j. A summary of concentrations of the SOA tracers together with the average contributions of their carbon contents to OC and WSOC in summer and autumn is provided in Table 1. All the SOA tracers including 2,3-DHOPA, except for a few cases, showed very consistent temporal variations with each other at both ND and HEP sites in both the seasons and peaked during 14-23 July in summer and were abundant during October, except for 2-MTLs and C5alkene triols, in autumn (Fig. 1e-j). However, their concentrations, except for a few cases, were slightly higher at HEP than those at ND in summer but comparable, except for PA, in autumn (Fig. 1e-j). Interestingly, the concentrations of 2-MTLs and C5-alkenes were very low from mid-September to October, whereas those of the remaining SOA tracers showed an increasing trend from late September and remained relatively high and stable during October, except for peaks in some cases (Fig. 1e-j). Such spatial and seasonal variations of SOA tracers during the campaign indicate that the

367 368 369 370 371 372 373 374 375 376 377 378

origins and formation processes of OA in the Tianjin region are different in summer and autumn. In fact, as noted earlier, the air masses that arrived in Tianjin mostly originated from oceanic regions in the summer, whereas in autumn, they mainly originated from Siberia passing over Mongolia and North China mainland (Fig. S2). They should have been enriched with marine biogenic VOCs in the summer and the VOCs emitted from higher plants, biomass burning and fossil fuel combustion in autumn, and they must have undergone aging during the long-range atmospheric transport. In addition, concentrations of O3 in the Tianjin atmosphere were higher in summer than in autumn whereas those of NO2 were higher in autumn than in summer (Fig. 1b), and a similar scenario might have prevailed at the regional scale. Such variations in oxidant loading must have played an important role in formation processes, and thus the loading of SOA tracers in each season. 2-MTLs are considered to be specific molecular tracers of isoprene photooxidation in the

379 380

ambient atmosphere.68 The 2-MTLS and C5-alkene triols are mainly formed by reactive uptake of isoprene epoxydiols (IEPOX) that are produced by the reaction of isoprene with OH and 12


Page 13 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60


381

HO2 radicals without the involvement of NOx.19, 21, 69 Besides, 2-MTLs could be produced by

382 383 384 385 386 387 388 389 390 391 392 393 394 395 396 397 398 399 400 401 402 403 404 405 406 407 408 409 410 411 412

isoprene ozonolysis in the presence of acidic aerosol70. On the other hand, isoprene can be oxidized to methacrolein through RO2+NO reaction under high NOx conditions, that further transforms into methacryloyl peroxynitrate (MPAN) upon oxidation with OH and NOx radicals.71, 72 MAPN may react with OH to form MGA and related compounds under acidic conditions through the intermediates: MAE22 and hydroxymethyl-methyl-lactone.73 The average concentration (8.05 ng m-3) of 2-MTLs at HEP was found to be higher by a factor of ~2 than that (4.13 ng m-3) at ND in summer. In autumn, their concentrations did not show any significant spatial variations and were lower by 2.7 and 6.5 times than those in summer at ND and HEP, respectively (Table 1). C5-alkene triols were found to be much higher in summer than that in autumn at both sites, with the highest average concentration of 20.11 ng m-3 at HEP in summer (Table 1). Similarly, concentrations of 2-MGA were slightly higher at HEP than those at ND in summer, but such differences were insignificant in autumn (Fig. 1f; Table 1). Sum of C5-alkene triols found to be the most abundant among all isoprene-derived SOA tracers followed by the sum of 2-MTLs and 2-MGA, respectively, at both the sites and seasons (Table 1), except in autumn at HEP, in which C5-alkene triols abundance was found to be the lowest (1.10±0.67 ng m-3). The high abundances of both 2-MTLs and C5-alkene triols in summer should have been driven by enhanced emission of isoprene from marine biota and terrestrial vegetation and its subsequent oxidation via HO2-channel under relatively low NOx conditions19-21 (Fig. 1b). Whereas in autumn, since the air masses that arrived in Tianjin originated from continental regions (Fig. S2), the isoprene contribution from marine biota might be insignificant, despite potential sea-breezes over Tianjin. On the other hand, the isoprene emission from higher plants must be reduced with decreasing ambient temperatures (Fig. 1a). In addition, the decrease in O3 and increase in NO2 concentrations (Fig. 1b) must have promoted the formation of 2-MGA via NO2-channel rather than 2-MTLs and C5-alkene triols in autumn.22 Furthermore, the higher levels of all the tracers at HEP than those at ND in summer is likely because the emission of isoprene from local vegetation under high ambient temperatures (Fig. 1a) and light must be high in HEP, while no spatial differences in autumn suggests that the influence of local biogenic emission might be insignificant and thus the long-range transported air masses might have played a major role.

413 414 415 416 417 418 419 420

The scatter plots between 2-methylthreitol and 2-methylerythritol as well as those between 2-MTLs and C5-alkene triol showed excellent linear relations with high correlation coefficients (r = 0.81 to 0.99) at both ND and HEP in both the seasons (see Fig. S3a,b). Such linear relations indicate that they should have been derived by similar formation processes in the respective seasons as discussed earlier. The concentration of 2-MGA has been reported to be one order lower than that of 2-MTLs and C5-alkene triols at low NOx sites in the US and Germany, as compared to 2-4 times at a rural site, Gucheng, in the North China Plain, where the influence of sulfate, aerosol acidity, and biomass burning was found to be significant15. Interestingly, 13



Page 14 of 27

421

concentrations of 2-MGA were found to be ~5 times lower than those of 2-MTLs at both the

422 423 424 425 426 427 428 429

sites and more than one order magnitude lower than those of C5-alkene triols at both the sites in summer whereas in autumn, they were almost similar to those of 2-MTLs at both the sites and those of C5-alkene triols at HEP (Table 1). Such lower levels of 2-MGA than 2-MTLs and C5-alkene triols further supports that the oxidation of isoprene via HO2-channel is dominant in summer. In comparison, their similar abundances in autumn implies that the influence of anthropogenic emissions, including biomass burning,9 should have a severe impact and the isoprene oxidation via NO2-channel must be dominant in autumn. SOAM tracers (PA, PNA, 3-HGA and 3-MBTCA) showed very consistent temporal

430 431 432 433 434 435 436 437 438 439 440 441 442 443

variations in summer at both ND and HEP, and they were similar to those of SOAI tracers, except for a very few cases (Fig. 1e-h). Whereas in autumn, the temporal trends of only PA and 3-HGA were found to be similar at both the sites, despite the lower levels of PA at HEP, and were comparable to that of 2-MGA (Fig. 1f-h). Those of PNA and 3-MBTCA were quite different from other SOAM and SOAI tracers (Fig. 1g,h). Furthermore, the scatter plots of 3HGA and 3-MBTCA, which are second-generation species of α-pinene, showed a strong linear relationship at both the sites (r = 0.82 at ND and 0.97 at HEP) in only summer, while the correlation coefficients were weak (r = 0.2 and 0.35, respectively) in autumn at both sites (Fig. S3c). Concentrations of PNA were higher in autumn than those in summer at both the sites (Table 1). In contrast, concentrations of PA in both the seasons were comparable at ND, but they were higher in summer than those in autumn at HEP (Table 1). Interestingly, both 3-HGA and 3-MBTCA concentrations were higher in summer than those in autumn at both the sites (Table 1). Such similarities in temporal trends of both first-generation (PNA and PA) and high-

444 445 446 447 448 449 450 451 452 453 454 455 456 457 458

generation (3-HGA and 3-MBTCA) tracers and strong correlations between the 3-HGA and 3MBTCA indicate that they should have been derived from photooxidation of monoterpenes by O3 and OH radicals28, 29 under low NOx conditions in summer. It is likely because the O3 concentrations were relatively higher and those of NO2 were lower in summer, as compared to those in autumn in the Tianjin atmosphere (Fig. 1b). Moreover, emission of monoterpenes from local vegetation and their subsequent in-situ photooxidation might be significant, in addition to the contributions from long-range transported air masses that originated from the oceanic regions in summer (Fig. S2a,b). In contrast, the differences in temporal trends of the SOAM tracers and weak correlations between the high-generation tracers in autumn suggest that they must be potentially influenced by additional sources, e.g., biomass burning and anthropogenic pollution, which could influence their formation processes and transformations in the atmosphere. The high abundance of 3-HGA and 3-MBTCA that were formed by photodegradation of PNA and PA30, 31 implies that the aging of OA was higher in summer than in autumn. β-CPA, the only SOAS tracer, also showed a very similar temporal trend with all other 14


Page 15 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60


459

tracers in summer at both the sites, whereas in autumn, the trend was similar to that of 2-MGA,

460 461 462 463 464 465 466 467 468 469 470 471 472

PA and 3-HGA as well as 2,3-DHOPA (Fig. 1f-j). Further, it was more abundant in autumn than in summer at both the sites and the concentration levels were slightly higher at HEP than those at ND (Table 1). It has been reported that because of the low volatility of sesquiterpenes, they could be accumulated in leaves and woods and abundantly emitted by biomass burning74. Also, based on the covariance of β-CPA with levoglucosan, it has been considered that the βCPA loading is increased with increasing biomass burning emissions.40, 75 Hence, the high abundance of β-CPA and its covariance with levoglucosan in Tianjin PM2.5 in autumn suggests that VOCs emitted from biomass burning should have played a prominent role in enhancing its loading in the Tianjin atmosphere rather than through biogenic emissions. The extremely low levels of 2-MTLs and C5-alkene triols in autumn also indicates that the contribution of SOA from biogenic emissions was low in autumn. Details of the possible influence of biomass burning is described in the next section. 2,3-DHOPA, the only SOAA tracer, showed very similar temporal variations, including

473 474 475 476 477 478 479 480 481 482 483 484 485 486 487 488 489

peaks during July and October, with those of all the biogenic SOA tracers in summer at both the sites (Fig. 1e-j). Such covariance might have been driven by high oxidation capacity of the atmosphere over Tianjin that results in the enhanced formation of SOA originating from both biogenic and anthropogenic origins. However, the concentrations of oxidants (e.g., O3 and NO2) in Tianjin were not enhanced during July 14-23, nor in October, corresponding to the peaks in SOA tracers, which suggests that the temporal trends of Tianjin OA might have mainly been influenced by long-range transported air masses rather than local emissions. Interestingly, the air masses that arrived in Tianjin in July mostly originated from the oceanic regions (Fig. S2a) that should have been enriched with marine biogenic emissions. Furthermore, the concentrations of 2,3-DHOPA were found to be higher at HEP, where the emission of biogenic VOCs should be higher, than those at ND where fossil fuel combustion should be relatively higher (Table 1; Fig. 1j). Surprisingly, in autumn, the temporal trend of 2,3-DHOPA was found to be extremely similar to that of β-CPA, 3-HGA and 2-MGA at ND and also at HEP, except for a few cases (Fig. 1f,h-j). These results suggest that DHOPA might be partly derived from biogenic and biomass burning emissions, rather than fossil fuel combustion alone. Such a possibility is discussed in the following sections. Mass ratios of first-generation to high-generation products such as (2-MTLS+C5-alkene

490 491 492 493 494 495 496

triols)/2-MGA and (PNA+PA)/(3-HGA+3-MBTCA) were 17.8  9.07 and 0.53  0.36 at ND and 18.1  10.8 and 0.35  0.08 at HEP, respectively, in summer and 4.38  3.63 and 0.81  0.42 at ND and 2.25  0.82 and 0.56 0.53 at HEP in autumn. Scatter plots between these mass ratios and ambient temperatures and RH at Tianjin were very scattered and did not show a linear relation, except between the (2-MTLS+C5-alkene triols)/2-MGA and temperature in summer at both the sites and at ND in autumn, as opposed to an inverse relation at HEP (Fig. S4). Such high mass ratios of (2-MTLS+C5-alkene triols)/2-MGA and linear relations with 15



497 498 499 500 501 502 503 504 505

Page 16 of 27

temperature indicate that the emission of BVOCs and subsequent in-situ photochemical Figure 3. Scatter plots between β-caryophyllinic acid and levoglucosan, a marker for biomass burning, at ND and HEP in Tianjin in summer (a) and autumn (b).

formation of SOA, particularly SOAI, at the local scale should be significant over Tianjin in summer. On the other hand, the lower (PNA+PA)/(3-HGA+3-MBTCA) ratios and their lack of relation with local meteorological parameters further suggest that the SOA loading over Tianjin was not only influenced by local biogenic emissions but also by the long-range transported air masses in both the seasons.

506

Enhanced contribution of biogenic VOCs in summer. Temporal variations of

507 508 509 510 511 512 513 514 515 516 517 518 519 520 521 522 523

SOA tracers, except for MTLs and C5-alkene triols in autumn (Fig. 1e-j), were consistent with not only those of WSOC and OC but also EC (Fig. 1c). Such comparability implies that the loading of SOA in Tianjin is mainly controlled by VOC emission strength rather than the local meteorology. However, the concentrations of all the SOA tracers, as well as WSOC, OC and even EC, were enhanced in the samples collected during 14-23 July at both sites in summer, although the increase in the EC level was not as high as WSOC or OC (Fig. 1c,e-j). Concentrations of a sum of hopanoid hydrocarbons (C27-32), molecular markers for fossil fuel combustion emissions,76, 77 were found to be very low and did not show any increase during these days, but levoglucosan, an excellent tracer for biomass burning64, levels were slightly enhanced during these days (Fig. 1d). Hence, biomass burning emissions might have caused the enhancement of EC levels, as well as organics, in summer. However, the loading of levoglucosan was much lower in summer (range, 0.77-26.9 ng m-3 at ND and 0.31-8.96 ng m3 at HEP) than in autumn (6.94-210 ng m-3 and 28.4-203 ng m-3, respectively), which implies that the emissions from biomass burning should be minor in summer. Hence, it is likely that the loading of organics over Tianjin in summer should have been mainly driven by biogenic emission of VOCs and their subsequent photooxidation. It has been well identified that increasing ambient temperature and solar intensity increases

524 525

the stress on higher plants and biological activity over the sea surface, and that it therefore enhances the emission of VOCs from terrestrial vegetation and marine biota in summer.11 16


Page 17 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60

526 527


Furthermore, increased ambient temperature and RH promotes the photochemical oxidation of Figure 4. Scatter plots of DHOPA with hopanes (a, b), levoglucosan (c, d) and β-caryophyllinic acid (e, f)

528 529 530

at ND and HEP in Tianjin in summer and autumn.

531 532 533 534 535 536 537 538 539 540 541 542

was relatively increased and RH was lower than 80% during 14-23 July (Fig. 1a), corresponding to the peaks in SOA tracers as well as OC and WSOC (Figs.1c,e-j). It is likely that the same scenario might have prevailed at regional scale. Scatter plots of total isopreneand α/β-pinene-derived SOA tracers with ambient temperature showed a linear relationship with weak to moderate correlation coefficients in both summer and autumn (Fig. S5). Whereas β-caryophyllinic acid and 2,3-DHOPA, except at ND, showed a linear relationship with temperature in summer and an inverse relationship in autumn (Fig. S5i,k,m,o). Interestingly, all the SOA tracers showed a linear relation with RH in autumn with weak to moderate correlation coefficients, in which the RH did not exceed 75%, (Fig. S5d,h,l,p), but not in summer (Fig. S5b,f,j,n). It is worthy to note that the data points showed a positive trend until the RH reaches 70% in summer, after that they were scattered (Fig. S5b,f,j,n). Such trends and linear relations imply that the enhanced emission and photochemical

543 544 545 546 547

oxidation of BVOCs are a significant source of SOA over Tianjin in summer, whereas in autumn, the SOA should be derived from other sources as well. On the other hand, the gas-toparticle partitioning might be significant in autumn. In summer, the gas-to-particle partitioning might be enhanced with increasing RH up to only ~75% and after that, the aqueous phase reactions may become more prominent resulting in the high-generation more oxygenated

VOCs and phase transition, respectively, to produce SOA. The ambient temperature in Tianjin

17



Page 18 of 27

548 549

products. Influence of biomass burning and fossil fuel combustion. To understand the role

550 551 552 553 554 555 556 557 558 559 560 561 562 563 564 565 566

of biomass burning and fossil fuel combustion emissions on SOA loading and its formation processes over Tianjin, we examined linear relations between SOA tracers and specific tracers: levoglucosan and hopanes, for the biomass burning64 and fossil fuel combustion,76, 77 respectively. We found that the scatter plots of both isoprene- and α/β-pinene-derived SOA tracers with levoglucosan were highly scattered and did not show any relation at either site in summer and autumn (Fig. S6). Although temporal variations of β-CPA (Fig. 1i) are not similar to those of levoglucosan, which were found to be significant only from early September and abundant during October (Fig. 1d), they showed linear relations with weak or moderate correlation coefficients at both the sites and in both the seasons (Fig. 3). Such linear relations suggest that β-CPA should have been partly derived from the VOCs emitted from biomass burning, particularly in autumn. On the other hand, the air masses that arrived in Tianjin originated from Siberia and passed over Mongolia and the mainland of northern China where possible biomass emissions, including crop waste burning, are high in autumn. Moreover, concentrations of NO2 increased in autumn compared to those in summer, and the temporal pattern (Fig. 1b) was very close to that of both levoglucosan and β-CPA (Fig. 1d,i), which further support our assumption that biomass burning emissions were significant in autumn. 2,3-DHOPA showed positive relations with hopanes at both the sites in both the seasons

567 568 569 570 571 572 573 574 575 576 577 578

but the correlation coefficients were weak or moderate (Fig. 4a,b). Interestingly, it also showed linear relations with levoglucosan with moderate to good correlation coefficients in both the seasons at ND and in summer at HEP (Fig. 4c,d). On the other hand, 2,3-DHOPA showed linear relationships with β-CPA with high correlation coefficients in both summer and autumn (Fig. 4e,f). These results, together with the covariance with biogenic SOA tracers, particularly in summer (Fig. 1e-j), suggest that 2,3-DHOPA in Tianjin PM2.5 should have been derived not only from fossil fuel combustion but also partly from biogenic emissions and biomass burning. It is likely because terrestrial higher plants,78 marine biota79 and wood combustion80 emit significant amounts of phenolic compounds that could produce the 2,3-DHOPA upon photooxidation in the atmosphere. However, such a possibility needs to be investigated further, a subject of future research. Contributions of SOA tracers to OC and WSOC. Contributions of total isoprene-

579 580

derived SOA tracers-C contents to OC and WSOC were found to be more abundant in summer at both ND (range, 0.07-1.16%, and 0.07-1.21%, respectively) and HEP (0.14-1.20% and 0.17-

581 582 583 584 585

1.15%) followed by those of α/β-pinene-derived SOA tracers (0.09-0.37% and 0.12-0.48% at ND and 0.09-0.29% and 0.11-0.29% at HEP, respectively), β-caryophyllinic acid and 2,3DHOPA, respectively (Table 1). Whereas in autumn, the contributions of α/β-pinene-derived SOA tracers-C in OC (0.06-0.21% at ND and 0.04-0.19% at HEP) and WSOC (0.09-0.32% and 0.06-0.37%, respectively) were abundant followed by those of isoprene-derived SOA 18


Page 19 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60


586

tracers (0.01-0.23% and 0.02-0.29% at ND and 0.01-0.07% and 0.03-0.13% at HEP,

587 588 589

Figure 5. Temporal variations in concentrations (g m-3) of SOC derived from isoprene (SOCI),

590 591 592 593 594 595 596 597 598 599 600 601 602 603 604 605 606 607 608

monoterpene (SOCM), sesquiterpene (SOCS) and aromatics (SOCA) (a) and their contributions to OC (b) and WSOC (c) in PM2.5 at ND and HEP in Tianjin during summer to autumn.

respectively), β-CPA and 2,3-DHOPA, respectively (Table 1). These trends indicate that isoprene-derived SOA tracers largely contribute to organics in summer, as opposed to monoterpene-derived SOA tracers in autumn over Tianjin. Source apportionment by SOA-tracer method. The SOA-tracer based method developed by Kleindienst et al.35 was applied to estimate the contributions of SOC derived from isoprene (SOCI), monoterpene (SOCM), sesquiterpene (SOCS) and aromatics (SOCA) using the measured concentrations of SOA tracers. A summary of the estimated SOCI, SOCM, SOCS and SOCA and their average contributions to OC and WSOC at ND and HEP in summer and autumn is provided in Table 1. Their temporal variations are depicted in Fig. 5. The SOCI ranged from 0.004 gC m-3 to 0.097 gC m-3 with an average of 0.024 ± 0.020 gC m-3 at ND and 0.005-0.183 gC m-3 (average 0.038 ± 0.048 gC m-3) at HEP. While the SOCM and SOCS were 0.016-0.086 gC m-3 (0.036 ± 0.017 gC m-3) and 0.015-0.251 gC m-3 (0.065 ± 0.048 g m-3) at ND 0.014-0.097 gC m-3 (0.039 ± 0.027 g m-3) and 0.024-0.202 gC m-3 (0.086 ± 0.054 gC m-3) at HEP, respectively. The SOCA was 0.029-0.774 gC m-3 (0.167 ± 0.152 gC m-3) at ND and 0.043-0.394 gC m-3 (0.218 ± 0.112 gC m-3) at HEP. SOCA was found to be the most abundant component that accounted for 45 ± 11% of total SOC at ND and 51 ± 12% at HEP in summer and 60 ± 10% and 63 ± 7%, respectively, in autumn followed by SOCS (25 ± 6% and 20 ± 8% in summer and 21 ± 3% and 25 ± 6% in autumn) at both the sites during the 19



Page 20 of 27

609

campaign. SOAM was the third most abundant (17 ± 5%) at ND in summer and at both the sites

610 611 612 613 614 615

(13 ± 8% and 8 ± 5%, respectively) in autumn, whereas SOAI was the third most abundant at HEP (15 ± 6%) in summer. These results indicate that the total biogenic SOC accounts for ~50% in summer and ~40% in autumn while the rest would be derived from aromatics of anthropogenic sources including biomass burning. However, the possible biogenic origin of 2,3-DHOPA and thus SOCA needs to be investigated further. The SOCI and SOCM loadings were higher at HEP than that at ND in summer, whereas in

616 617 618 619 620 621 622 623 624 625 626 627 628 629 630 631 632 633 634

autumn, they did not show any significant spatial variation but were much lower as compared to summer (Table 1). In contrast, both SOCS and SOCA were higher in autumn than in summer at both the sites and were also higher at HEP than at ND in both the seasons (Table 1). Although the temporal variations in SOC were peaked in mid-July in summer and during October in autumn, their contributions to OC and WSOC were relatively stable: accounting for ~10% and ~15%, respectively, during the whole campaign period except for a few cases (Fig. 5). This suggests that SOA formation is always significant and plays a major role in driving the OA burden in the Tianjin region. The contribution of total SOC (SOCTotal) ranged from 5.06%to 18.4% with an average of 10.5 ± 3.76% to OC at ND, 5.59-23.7% (average 14.8 ± 5.97%) at HEP in summer and 4.16-12.7 (8.31 ± 2.45%) and 5.21-10.3% (7.89 ± 1.77%), respectively, in autumn. While the contributions of SOCTotal to WSOC were 6.28-23.2% (12.2 ± 4.21%) at ND and 6.84-30.7% (17.1 ± 7.09%) at HEP in summer and 6.46-17.5% (11.8 ± 3.32%) and 8.64-21.3% (13.9 ± 3.32%), respectively, in autumn. Thus, it is clear that the contributions of SOC to both WSOC and OC are significant over the Tianjin region and enhanced in summer due to increased emissions of biogenic VOCs and photochemical activity due to high ambient temperatures and solar intensity in summer.

635 636 637 638 639 640 641 642 643 644 645 646

including 2,3-DHOPA at both sites with peaks during 14-23 July, corresponding to high ambient temperatures in Tianjin, and their relatively high abundance at a background site (HEP) as compared to an urban site (ND) implied that biogenic emissions from local vegetation and subsequent SOA formation were high in summer. While the high loadings of all the tracers, except for 2-MTLs and C5-alkene triols, during October, corresponding to levoglucosan, a marker of biomass burning, indicate that the contributions of the SOA derived from the biomass burning emissions were significant in autumn. The relations between 2,3-DHOPA and hopanes, and no relations of the mass ratios of first- to high-generation SOA tracers and meteorological parameters suggested that the contributions from anthropogenic aromatics and aging of OA during long-range transport over the Tianjin region were significant in both seasons. The estimated contributions of SOC indicated that the SOC derived from anthropogenic aromatics was abundant (~50% in summer and ~60% in autumn) over Tianjin,

CONCLUSIONS The consistent temporal variations, except for a few cases, of all the measured SOA tracers

20


Page 21 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60


647

North China. Based on the covariance of 2,3-DHOPA with biogenic SOA tracers, and the linear

648 649 650 651 652 653 654 655 656 657 658 659 660

relation with β-CPA together with its high abundance at HEP and origins of the air masses arrived in Tianjin, we conclude that the 2,3-DHOPA was partly derived from biogenic and biomass burning emissions. However, it needs to be confirmed through further investigation, a subject of future research.

661

*Phone:

662

ORCID

663 664 665 666 667 668 669 670 671 672 673 674 675 676 677 678 679 680 681 682 683 684 685 686 687

Chandra Mouli Pavuluri: 0000-0002-2955-474X Pingqing Fu: 0000-0001-6249-2280 Yan-Lin Zhang: 0000-0002-8722-8635 Notes The authors declare no competing financial interest.

ASSOCIATED CONTENT Supplementary information Map of China with sampling sites, air mass trajectories, and scatter plots of selected SOA tracers verses the tracers and levoglucosan, and those of tracers as well as their mass ratios and ambient temperature and RH (Figs. S1-S6). AUTHOR INFORMATION Corresponding Author +86 22 87370995. E-mail: [email protected].

ACKNOWLEDGEMENTS This study was in part supported by The National Natural Science Foundation of China through Grant-in-Aid numbers: 41775120 and 91644103, and the National Key R&D Program of China (2017YFC0212700). REFERENCES 1.

Kanakidou, M.;

Seinfeld, J. H.;

Dingenen, R.;

Ervens, B.;

S.;

Moortgat, G. K.;

Horth, J.;

Nenes, A.;

Pandis, S. N.; Nielsen, C. J.;

Winterhalter, R.;

Barnes, I.;

Dentener, F. J.;

Swietlicki, E.;

Putaud, J. P.;

Myhre, C. E. L.;

Tsigaridis, K.;

Facchini, M. C.; Balkanski, Y.;

Vignati, E.;

Van

Fuzzi,

Stephanou,

E. G.; Wilson, J., Organic aerosol and global climate modelling: a review. Atmospheric Chemistry and Physics 2005, 5, 1053-1123. 2.

Ramanathan, V.;

Crutzen, P. J.;

Kiehl, J. T.; Rosenfeld, D., Aerosols, Climate, and the Hydrological

Cycle. Science 2001, 294, 2119-2124. 3.

Baltensperger, U.;

Facchini, M. C.; B.;

Dommen, J.;

Decesari, S.;

Puxbaum, H.;

Finessi, E.;

Geiser, M.;

Savi, M.;

Alfarra, R.; Reinnig, C.; Lang, D.;

Duplissy, J.; Schott, M.;

Gaeggeler, K.;

Warnke, J.;

Metzger, A.;

Hoffmann, T.;

Klatzer,

Kalberer, M.; Geiser, T., Combined determination of

the chemical composition and of health effects of secondary organic aerosols: The POLYSOA project. J Aerosol Med Pulm D 2008, 21 (1), 145-154. 4.

Tuet, W. Y.;

Chen, Y. L.;

Fok, S.;

Champion, J. A.; Ng, N. L., Inflammatory responses to secondary 21



688 689 690 691 692 693 694 695 696 697 698 699 700 701 702 703 704 705 706 707 708 709 710 711 712 713 714 715 716 717 718 719 720 721 722 723 724 725 726 727 728 729

Page 22 of 27

organic aerosols (SOA) generated from biogenic and anthropogenic precursors. Atmos Chem Phys 2017, 17 (18), 11423-11440. 5.

Andreae, M. O.; Crutzen, P. J., Atmospheric aerosols: Biogeochemical sources and role in atmospheric

chemistry. Science 1997, 276 (5315), 1052-1058. 6.

Fu, T. M.;

Jacob, D. J.;

Wittrock, F.;

Burrows, J. P.;

Vrekoussis, M.; Henze, D. K., Global budgets

of atmospheric glyoxal and methylglyoxal, and implications for formation of secondary organic aerosols. J Geophys Res-Atmos 2008, 113 (D15), D15303. 7. A. P.;

Robinson, A. L.; Lane, T. E.;

Donahue, N. M.;

Shrivastava, M. K.;

Weitkamp, E. A.;

Sage, A. M.;

Grieshop,

Pierce, J. R.; Pandis, S. N., Rethinking organic aerosols: Semivolatile emissions and

photochemical aging. Science 2007, 315 (5816), 1259-1262. 8.

Hallquist, M.;

Wenger, J. C.;

Baltensperger, U.; Rudich, Y., The formation, properties and impact

of secondary organic aerosol: current and emerging issues. Atmospheric Chemistry and Physics 2009, 9, 51555236. 9.

Ding, X.;

He, Q. F.;

Shen, R. Q.;

Yu, Q. Q.;

Zhang, Y. Q.;

Xin, J. Y.;

Wen, T. X.; Wang, X. M.,

Spatial and seasonal variations of isoprene secondary organic aerosol in China: Significant impact of biomass burning during winter. Sci Rep-Uk 2016, 6, 20411. 10. Ding, X.; Hu, Q. H.;

Zhang, Y. Q.;

Wang, Y. S.;

He, Q. F.;

Li, L. F.;

Yu, Q. Q.;

Shen, R. Q.;

Zhang, Y. L.;

Zhang, Z.;

Lyu, S. J.;

Song, W.; Wang, X. M., Spatial and seasonal variations of secondary organic

aerosol from terpenoids over China. J Geophys Res-Atmos 2016, 121 (24), 14661-14678. 11. Guenther, A.; LKlinger, L.;

Hewitt, C. N.;

Lerdau, M.;

Erickson, D.;

McKay, W. A.;

Pierce, T.;

Fall, R.;

Geron, C.;

Scholes, B.;

Graedel, T.;

Steinbrecher, R.;

Harley, P.;

Tallamraju, R.;

Taylor, J.; Zimmerman, P., A global model of natural volatile organic compound emissions. Journal of Geophysical Research 1995, 100, 8873-8892. 12. Guenther, A.;

Karl, T.;

Harley, P.;

Wiedinmyer, C.;

Palmer, P. I.; Geron, C., Estimates of global

terrestrial isoprene emissions using MEGAN (Model of Emissions of Gases and Aerosols from Nature). Atmospheric Chemistry and Physics 2006, 6, 3181-3210. 13. Piccot, S.;

Watson, J. G.; Jones, J., A global inventory of volatile organic compound emissions from

anthropogenic sources. Journal of Geophysical Research 1992, 97 (D9), 9897-9912. 14. de Gouw, J.; Jimenez, J. L., Organic Aerosols in the Earth's Atmosphere. Environ Sci Technol 2009, 43 (20), 7614-7618. 15. Li, J. J.;

Wang, G. H.;

Wu, C.;

Cao, C.;

Ren, Y. Q.;

Wang, J. Y.;

Li, J.;

Cao, J. J.;

Zeng, L. M.;

Zhu, T., Characterization of isoprene-derived secondary organic aerosols at a rural site in North China Plain with implications for anthropogenic pollution effects. Sci Rep-Uk 2018, 8, 535. 16. Hoyle, C. R.; Hartz, K. H.;

Boy, M.;

Petters, M. D.;

Donahue, N. M.;

Petaja, T.;

Fry, J. L.;

Glasius, M.;

Guenther, A.;

Hallar, A. G.;

Rosenoern, T.; Sullivan, A. P., A review of the anthropogenic

influence on biogenic secondary organic aerosol. Atmospheric Chemistry and Physics 2011, 11 (1), 321-343. 17. Pandis, S. N.;

Paulson, S. E.;

Seinfeld, J. H.; Flagan, R. C., Aerosol formation in the photooxidation

of isoprene and β-pinene. Atmospheric Environment 1991, 25A, 997-1008. 18. Claeys, M.; Guyon, P.;

Graham, B.;

Andreae, M. O.;

Vas, G.;

Wang, W.;

Vermeylen, R.;

Pashynska, V.;

Cafmeyer, J.;

Artaxo, P.; Maenhaut, W., Formation of secondary organic aerosols through

photooxidation of isoprene. Science 2004, 303 (5661), 1173-1176. 19. Paulot, F.;

Crounse, J. D.;

Kjaergaard, H. G.;

Kurten, A.;

St Clair, J. M.;

Seinfeld, J. H.;

22


Page 23 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60

730 731 732 733 734 735 736 737 738 739 740 741 742 743 744 745 746 747 748 749 750 751 752 753 754 755 756 757 758 759 760 761 762 763 764 765 766 767 768 769 770 771


Wennberg, P. O., Unexpected Epoxide Formation in the Gas-Phase Photooxidation of Isoprene. Science 2009, 325 (5941), 730-733. 20. Lin, Y. H.; Shaw, S. L.;

Zhang, Z.;

Knipping, E. M.;

Docherty, K. S.;

Edgerton, E. S.;

Zhang, H.;

Budisulistiorini, S. H.;

Kleindienst, T. E.;

Rubitschun, C. L.;

Gold, A.; Surratt, J. D., Isoprene epoxydiols

as precursors to secondary organic aerosol formation: acid-catalyzed reactive uptake studies with authentic compounds. Environ Sci Technol 2012, 46 (1), 250-8. 21. Surratt, J. D.; S. P.;

Chan, A. W. H.;

Flagan, R. C.;

Eddingsaas, N. C.;

Chan, M. N.;

Loza, C. L.;

Kwan, A. J.;

Hersey,

Wennberg, P. O.; Seinfeld, J. H., Reactive intermediates revealed in secondary organic

aerosol formation from isoprene. P Natl Acad Sci USA 2010, 107 (15), 6640-6645. 22. Lin, Y. H.; T. Q.; O.;

Zhang, H. F.;

Budisulistiorini, H.; Bartolotti, L. J.;

Pye, H. O. T.;

Sexton, K. G.;

Zhang, Z. F.;

Vizuete, W.;

Marth, W. J.;

Xie, Y.;

Park, S.;

Luecken, D. J.;

Arashiro, M.;

Piletic, I. R.;

Cui,

Edney, E.

Gold, A.; Surratt, J. D., Epoxide as a precursor to secondary organic aerosol formation

from isoprene photooxidation in the presence of nitrogen oxides. P Natl Acad Sci USA 2013, 110 (17), 67186723. 23. Zhang, H.;

Surratt, J. D.;

Lin, Y. H.;

Bapat, J.; Kamens, R. M., Effect of relative humidity on SOA

formation from isoprene/NO photooxidation: enhancement of 2-methylglyceric acid and its corresponding oligoesters under dry conditions. Atmospheric Chemistry and Physics 2011, 11 (13), 6411-6424. 24. Surratt, J. D.;

Lewandowski, M.;

Offenberg, J. H.;

Jaoui, M.;

Kleindienst, T. E.;

Edney, E. O.;

Seinfeld, J. H., Effect of acidity on secondary organic aerosol formation from isoprene. Environmental Science & Technology 2007, 41 (15), 5363-5369. 25. Carlton, A. G.;

Wiedinmyer, C.; Kroll, J. H., A review of Secondary Organic Aerosol (SOA) formation

from isoprene. Atmospheric Chemistry and Physics 2009, 9 (14), 4987-5005. 26. Heald, C. L.; P. G.;

Vitt, F.;

Henze, D. K.;

Seinfeld, J. H.;

Horowitz, L. W.;

Feddema, J.;

Lamarque, J. F.;

Guenther, A.;

Hess,

Goldstein, A. H.; Fung, I., Predicted change in global secondary organic aerosol

concentrations in response to future climate, emissions, and land use change. J Geophys Res-Atmos 2008, 113 (D5), D05211. 27. Kanakidou, M.;

Seinfeld, J. H.; Pandis, S. N., Organic aerosol and global climate modelling, a

review.pdf. Atmospheric Chemistry and Physics 2005, 5, 1053-1123. 28. Jenkin, M. E.;

Shallcross, D. E.; Harvey, J. N., Development and application of a possible mechanism

for the generation of cis-pinic acid from the ozonolysis of alpha- and beta-pinene. Atmos Environ 2000, 34 (18), 2837-2850. 29. Larsen, B. R.;

Di Bella, D.;

Glasius, M.;

Winterhalter, R.;

Jensen, N. R.; Hjorth, J., Gas-phase OH

oxidation of monoterpenes: Gaseous and particulate products. J Atmos Chem 2001, 38 (3), 231-276. 30. Muller, L.;

Reinnig, M. C.;

Naumann, K. H.;

Saathoff, H.;

Mentel, T. F.;

Donahue, N. M.;

Hoffmann, T., Formation of 3-methyl-1,2,3-butanetricarboxylic acid via gas phase oxidation of pinonic acid - a mass spectrometric study of SOA aging. Atmos Chem Phys 2012, 12 (3), 1483-1496. 31. Claeys, M.; Jaoui, M.;

Szmigielski, R.;

Kleindienst, T. E.;

Kourtchev, I.;

Lewandowski, M.;

Van der Veken, P.;

Vermeylen, R.;

Maenhaut, W.;

Offenberg, J. H.; Edney, E. O., Hydroxydicarboxylic acids:

Markers for secondary organic aerosol from the photooxidation of alpha-pinene. Environ Sci Technol 2007, 41 (5), 1628-1634. 32. Jaoui, M.;

Lewandowski, M.;

Kleindienst, T. E.;

Offenberg, J. H.; Edney, E. O., beta-caryophyllinic

acid: An atmospheric tracer for beta-caryophyllene secondary organic aerosol. Geophys Res Lett 2007, 34 (5),

23



772 773 774 775 776 777 778 779 780 781 782 783 784 785 786 787 788 789 790 791 792 793 794 795 796 797 798 799 800 801 802 803 804 805 806 807 808 809 810 811 812 813

Page 24 of 27

L05816. 33. Hallquist, M.; Dommen, J.;

Wenger, J. C.;

Donahue, N. M.;

T.;

Iinuma, Y.;

Jang, M.;

G.;

Mentel, T. F.;

Baltensperger, U.;

George, C.;

Jenkin, M. E.;

Monod, A.;

Rudich, Y.;

Goldstein, A. H.; Jimenez, J. L.;

Prevot, A. S. H.;

Simpson, D.;

Claeys, M.;

Hamilton, J. F.;

Herrmann, H.;

Hoffmann,

Kiendler-Scharr, A.;

Maenhaut, W.;

McFiggans,

Seinfeld, J. H.;

Surratt, J. D.;

Szmigielski, R.; Wildt, J.,

The formation, properties and impact of secondary organic aerosol: current and emerging issues. Atmospheric Chemistry and Physics 2009, 9 (14), 5155-5236. 34. Offenberg, J. H.;

Lewis, C. W.;

Lewandowski, M.;

Jaoui, M.;

Kleindienst, T. E.; Edney, E. O.,

Contributions of toluene and alpha-pinene to SOA formed in an irradiated toluene/alpha-pinene/NOx/air mixture: Comparison of results using C-14 content and SOA organic tracer methods. Environ Sci Technol 2007, 41 (11), 3972-3976. 35. Kleindienst, T. E.;

Jaoui, M.;

Lewandowski, M.;

Offenberg, J. H.;

Lewis, C. W.;

Bhave, P. V.;

Edney, E. O., Estimates of the contributions of biogenic and anthropogenic hydrocarbons to secondary organic aerosol at a southeastern US location. Atmospheric Environment 2007, 41 (37), 8288-8300. 36. Ding, X.;

He, Q. F.;

Shen, R. Q.;

Yu, Q. Q.; Wang, X. M., Spatial distributions of secondary organic

aerosols from isoprene, monoterpenes, beta-caryophyllene, and aromatics over China during summer. J Geophys Res-Atmos 2014, 119 (20), 11877-11891. 37. Kavouras, I. G.;

Mihalopoulos, N.; Stephanou, E. G., Formation of atmospheric particles from organic

acids produced by forests. Nature 1998, 395 (6703), 683-686. 38. Cahill, T. M.;

Seaman, V. Y.;

Charles, M. J.;

Holzinger, R.; Goldstein, A. H., Secondary organic

aerosols formed from oxidation of biogenic volatile organic compounds in the Sierra Nevada Mountains of California. J Geophys Res-Atmos 2006, 111 (D16), D16312. 39. Wang, W.; G. Y.;

Wu, M. H.;

Li, L.;

Zhang, T.;

Liu, X. D.;

Feng, J. L.;

Li, H. J.;

Wang, Y. J.;

Sheng,

Claeys, M.; Fu, J. M., Polar organic tracers in PM2.5 aerosols from forests in eastern China. Atmospheric

Chemistry and Physics 2008, 8 (24), 7507-7518. 40. Fu, P.;

Kawamura, K.;

Kanaya, Y.; Wang, Z., Contributions of biogenic volatile organic compounds

to the formation of secondary organic aerosols over Mt. Tai, Central East China. Atmospheric Environment 2010, 44 (38), 4817-4826. 41. Fu, P. Q.; Kawamura, K., Diurnal variations of polar organic tracers in summer forest aerosols: A case study of a Quercus and Picea mixed forest in Hokkaido, Japan. Geochem J 2011, 45 (4), 297-308. 42. Shen, R. Q.;

Ding, X.;

He, Q. F.;

Cong, Z. Y.;

Yu, Q. Q.; Wang, X. M., Seasonal variation of

secondary organic aerosol tracers in Central Tibetan Plateau. Atmospheric Chemistry and Physics 2015, 15 (15), 8781-8793. 43. Hu, D.;

Bian, Q.;

Li, T. W. Y.;

Lau, A. K. H.; Yu, J. Z., Contributions of isoprene, monoterpenes,

beta-caryophyllene, and toluene to secondary organic aerosols in Hong Kong during the summer of 2006. J Geophys Res-Atmos 2008, 113, D22206. 44. Ding, X.;

Zheng, M.;

Yu, L. P.;

Zhang, X. L.;

Weber, R. J.;

Yan, B.;

Russell, A. G.;

Edgerton,

E. S.; Wang, X. M., Spatial and seasonal trends in biogenic secondary organic aerosol tracers and water-soluble organic carbon in the southeastern United States. Environmental Science & Technology 2008, 42 (14), 5171-5176. 45. Fu, P. Q.;

Kawamura, K.;

Pavuluri, C. M.;

Swaminathan, T.; Chen, J., Molecular characterization

of urban organic aerosol in tropical India: contributions of primary emissions and secondary photooxidation. Atmospheric Chemistry and Physics 2010, 10, 2663-2689.

24


Page 25 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60

814 815 816 817 818 819 820 821 822 823 824 825 826 827 828 829 830 831 832 833 834 835 836 837 838 839 840 841 842 843 844 845 846 847 848 849 850 851 852 853 854 855


46. Fu, P. Q.;

Kawamura, K.;

Chen, J.; Barrie, L. A., Isoprene, Monoterpene, and Sesquiterpene

Oxidation Products in the High Arctic Aerosols during Late Winter to Early Summer. Environmental Science & Technology 2009, 43 (11), 4022-4028. 47. Chai, F. H.;

Gao, J.;

Chen, Z. X.;

Wang, S. L.;

Zhang, Y. C.;

Zhang, J. Q.;

Zhang, H. F.;

Yun,

Y. R.; Ren, C., Spatial and temporal variation of particulate matter and gaseous pollutants in 26 cities in China. J Environ Sci-China 2014, 26 (1), 75-82. 48. Huang, R. J.; Slowik, J. G.; Ciarelli, G.; Z. S.;

Zhang, Y. L.;

Platt, S. M.;

Canonaco, F.;

Piazzalunga, A.;

Szidat, S.;

Bozzetti, C.;

Zotter, P.;

Schwikowski, M.;

Baltensperger, U.;

Ho, K. F.;

Cao, J. J.;

Wolf, R.;

Han, Y. M.;

Pieber, S. M.;

Abbaszade, G.;

Daellenbach, K. R.;

Bruns, E. A.;

Schnelle-Kreis, J.;

Crippa, M.;

Zimmermann, R.;

An,

El Haddad, I.; Prevot, A. S. H., High secondary aerosol contribution to

particulate pollution during haze events in China. Nature 2014, 514 (7521), 218-222. 49. Jiang, F.;

Liu, Q.;

Huang, X. X.;

Wang, T. J.;

Zhuang, B. L.; Xie, M., Regional modeling of

secondary organic aerosol over China using WRF/Chem. Journal of Aerosol Science 2012, 43 (1), 57-73. 50. Fu, T. M.; Zhang, R.;

Cao, J. J.;

Wang, Y. X.;

Zhang, X. Y.;

Lee, S. C.;

Zhang, Q.;

Han, Y. M.;

Qu, W. J.;

Han, Z.;

Chen, D.; Henze, D. K., Carbonaceous aerosols in China: top-down constraints on

primary sources and estimation of secondary contribution. Atmospheric Chemistry and Physics 2012, 12 (5), 2725-2746. 51. Guo, S.;

Hu, M.;

Guo, Q. F.;

Zhang, X.;

Zheng, M.;

Zheng, J.;

Chang, C. C.;

Schauer, J. J.;

Zhang, R. Y., Primary Sources and Secondary Formation of Organic Aerosols in Beijing, China. Environ Sci Technol 2012, 46 (18), 9846-9853. 52. Yang, F.;

Kawamura, K.;

Chen, J.;

Ho, K.;

Lee, S.;

Gao, Y.;

Cui, L.;

Wang, T.; Fu, P. Q.,

Anthropogenic and biogenic organic comounds in summertime fine aerosols (PM2.5) in Beijing, China. Atmos Environ 2016, 124, 166-175. 53. Kong, S. F.;

Han, B.;

Bai, Z. P.;

Chen, L.;

Shi, J. W.; Xu, Z., Receptor modeling of PM2.5, PM10

and TSP in different seasons and long-range transport analysis at a coastal site of Tianjin, China. Sci Total Environ 2010, 408 (20), 4681-4694. 54. Li, P. H.;

Han, B.;

Huo, J.;

Lu, B.;

Ding, X.;

Chen, L.;

Kong, S. F.;

Bai, Z. P.; Wang, B.,

Characterization, Meteorological Influences and Source Identification of Carbonaceous Aerosols during the Autumn-winter Period in Tianjin, China. Aerosol Air Qual Res 2012, 12 (2), 283-294. 55. Li, X.; Geng, G. N.;

Zhang, Q.;

Zhang, Y.;

Wallington, T. J.;

Zhang, L.;

Han, W. J.;

Wang, Y. X.;

Zhang, Q. Q.;

Li, M.;

Zheng, Y. X.;

Shen, W.; He, K. B., Attribution of PM2.5 exposure in Beijing-

Tianjin-Hebei region to emissions: implication to control strategies. Sci Bull 2017, 62 (13), 957-964. 56. Chow, J. C.;

Watson, J. G.;

Chen, L. W. A.;

Chang, M. C. O.;

Robinson, N. F.;

Trimble, D.; Kohl,

S., The IMPROVE-A temperature protocol for thermal/optical carbon analysis: maintaining consistency with a long-term database. J Air Waste Manage 2007, 57 (9), 1014-1023. 57. Pavuluri, C. M.;

Kawamura, K.;

Aggarwal, S. G.; Swaminathan, T., Characteristics, seasonality and

sources of carbonaceous and ionic components in the tropical aerosols from Indian region. Atmospheric Chemistry and Physics 2011, 11 (15), 8215-8230. 58. Kleindienst, T. E.;

Lewandowski, M.;

Offenberg, J. H.;

Jaoui, M.; Edney, E. O., The formation of

secondary organic aerosol from the isoprene plus OH reaction in the absence of NOx. Atmospheric Chemistry and Physics 2009, 9 (17), 6541-6558. 59. Wang, S.;

Pavuluri, C. M.;

Ren, L. J.;

Fu, P. Q.;

Zhang, Y. L.; Liu, C. Q., Implications for

25



856 857 858 859 860 861 862 863 864 865 866 867 868 869 870 871 872 873 874 875 876 877 878 879 880 881 882 883 884 885 886 887 888 889 890 891 892 893 894 895 896 897

Page 26 of 27

biomass/coal combustion emissions and secondary formation of carbonaceous aerosols in North China. Rsc Adv 2018, 8 (66), 38108-38117. 60. Zheng, B.; Qi, J.;

Yan, L.;

Tong, D.;

Zhang, Y. X.;

Li, M.;

Liu, F.;

Zhao, H. Y.;

Hong, C. P.;

Zheng, Y. X.;

Geng, G. N.;

Li, H. Y.;

Li, X.;

Peng, L. Q.;

He, K. B.; Zhang, Q., Trends in China's

anthropogenic emissions since 2010 as the consequence of clean air actions. Atmospheric Chemistry and Physics 2018, 18 (19), 14095-14111. 61. Mayol-Bracero, O. L.; Facchini, M. C.;

Guyon, P.;

Graham, B.;

Roberts, G.;

Andreae, M. O.;

Decesari, S.;

Fuzzi, S.; Artaxo, P., Water-soluble organic compounds in biomass burning aerosols over

Amazonia - 2. Apportionment of the chemical composition and importance of the polyacidic fraction. J Geophys Res-Atmos 2002, 107 (D20), 8091. 62. Miyazaki, Y.; M.;

Kondo, Y.;

Takegawa, N.;

Komazaki, Y.;

Fukuda, M.;

Kawamura, K.;

Mochida,

Okuzawa, K.; Weber, R. J., Time-resolved measurements of water-soluble organic carbon in Tokyo. J

Geophys Res-Atmos 2006, 111 (D23), D23206. 63. Aggarwal, S. G.; Kawamura, K., Carbonaceous and inorganic composition in long-range transported aerosols over northern Japan: Implication for aging of water-soluble organic fraction. Atmos Environ 2009, 43 (16), 2532-2540. 64. Simoneit, B. R. T., Biomass burning - A review of organic tracers for smoke from incomplete combustion. Appl Geochem 2002, 17 (3), 129-162. 65. Feng, T.; Wang, Y. C.;

Zhao, S. Y.;

Zhou, W. J.;

Bei, N. F.;

Wu, J. R.;

Liu, S. X.;

Li, X.;

Liu, L.;

Qian, Y.;

Yang, Q. C.;

Cao, J. J.; Li, G. H., Secondary organic aerosol enhanced by increasing atmospheric

oxidizing capacity in Beijing-Tianjin-Hebei (BTH), China. Atmos Chem Phys 2019, 19 (11), 7429-7443. 66. Fu, P.; Kawamura, K., Diurnal variations of polar organic tracers in summer forest aerosols: A case study of a Quercus and Picea mixed forest in Hokkaido, Japan. Geochemical Journal 2011, 45 (45), 297-308. 67. Zhu, C.;

Kawamura, K.; Fu, P., Seasonal variations of biogenic secondary organic aerosol tracers in

Cape Hedo, Okinawa. Atmospheric Environment 2016, 130, 113-119. 68. Magda, C.;

Bim, G.;

Gyorgy, V.;

Wu, W.;

Reinhilde, V.;

Vlada, P.;

Jan, C.;

Pascal, G.;

Andreae, M. O.; Paulo, A., Formation of secondary organic aerosols through photooxidation of isoprene. Science 2004, 303 (5661), 1173-1176. 69. Lin, Y. H.; Shaw, S. L.;

Zhang, Z. F.;

Knipping, E. M.;

Docherty, K. S.;

Edgerton, E. S.;

Zhang, H. F.;

Kleindienst, T. E.;


Rubitschun, C. L.;

Gold, A.; Surratt, J. D., Isoprene Epoxydiols

as Precursors to Secondary Organic Aerosol Formation: Acid-Catalyzed Reactive Uptake Studies with Authentic Compounds. Environmental Science & Technology 2012, 46 (1), 250-258. 70. Riva, M.;


Zhang, Z. F.;

Gold, A.; Surratt, J. D., Chemical characterization of

secondary organic aerosol constituents from isoprene ozonolysis in the presence of acidic aerosol. Atmospheric Environment 2016, 130, 5-13. 71. Kroll, J. H.;

Ng, N. L.;

Murphy, S. M.;

Flagan, R. C.; Seinfeld, J. H., Secondary organic aerosol

formation from isoprene photooxidation. Environmental Science & Technology 2006, 40 (6), 1869-1877. 72. Surratt, J. D.; Szmigielski, R.;

Murphy, S. M.;

Vermeylen, R.;

Kroll, J. H.;

Maenhaut, W.;

Ng, N. L.;

Claeys, M.;

Hildebrandt, L.;

Sorooshian, A.;

Flagan, R. C.; Seinfeld, J. H., Chemical

composition of secondary organic aerosol formed from the photooxidation of isoprene. J Phys Chem A 2006, 110 (31), 9665-9690. 73. Nguyen, T. B.;

Bates, K. H.;

Crounse, J. D.;

Schwantes, R. H.;

Zhang, X.;

Kjaergaard, H. G.;

26


Page 27 of 27 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60

898 899 900 901 902 903 904 905 906 907 908 909 910 911 912 913 914 915 916 917 918 919 920


Surratt, J. D.;

Lin, P.;

Laskin, A.;

Seinfeld, J. H.; Wennberg, P. O., Mechanism of the hydroxyl radical

oxidation of methacryloyl peroxynitrate (MPAN) and its pathway toward secondary organic aerosol formation in the atmosphere. Physical Chemistry Chemical Physics 2015, 17 (27), 17914-17926. 74. Ciccioli, P.;

Centritto, M.; Loreto, F., Biogenic volatile organic compound emissions from vegetation

fires. Plant Cell Environ 2014, 37 (8), 1810-1825. 75. Haque, M. M.;

Kawamura, K.; Kim, Y., Seasonal variations of biogenic secondary organic aerosol

tracers in ambient aerosols from Alaska. Atmospheric Environment 2016, 130, 95-104. 76. Schauer, J. J.;

Kleeman, M. J.;

Cass, G. R.; Simoneit, B. R. T., Measurement of emissions from air

pollution sources. 2. C-1 through C-30 organic compounds from medium duty diesel trucks. Environ Sci Technol 1999, 33 (10), 1578-1587. 77. Schauer, J. J.;

Kleeman, M. J.;

Cass, G. R.; Simoneit, B. R. T., Measurement of emissions from air

pollution sources. 5. C-1-C-32 organic compounds from gasoline-powered motor vehicles. Environ Sci Technol 2002, 36 (6), 1169-1180. 78. Oros, D. R.; Simoneit, B. R. T., Identification and emission factors of molecular tracers in organic aerosols from biomass burning Part 1. Temperate climate conifers. Appl Geochem 2001, 16 (13), 1513-1544. 79. Bahadur, R.;

Uplinger, T.;

Russell, L. M.;

Sive, B. C.;

Cliff, S. S.;

Millet, D. B.;

Goldstein, A.;

Bates, T. S., Phenol groups in northeastern U.S. submicrometer aerosol particles produced from seawater sources. Environ Sci Technol 2010, 44 (7), 2542-2548. 80. Fine, P. M.;

Cass, G. R.; Simoneit, B. R. T., Chemical characterization of fine particle emissions from

the fireplace combustion of wood types grown in the Midwestern and Western United States. Environ Eng Sci 2004, 21 (3), 387-409.

TOC Graphic.

921

27


Characterization of Secondary Organic Aerosol Tracers Over Tianjin

Recommend Documents